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The Role of Crustal and Eruptive Processes Versus Source Variations in Controlling the Oxidation State of Iron in Central Andean Magmas ∗ Stephanie B

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The Role of Crustal and Eruptive Processes Versus Source Variations in Controlling the Oxidation State of Iron in Central Andean Magmas ∗ Stephanie B Earth and Planetary Science Letters 440 (2016) 92–104 Contents lists available at ScienceDirect Earth and Planetary Science Letters www.elsevier.com/locate/epsl The role of crustal and eruptive processes versus source variations in controlling the oxidation state of iron in Central Andean magmas ∗ Stephanie B. Grocke a,b, , Elizabeth Cottrell a, Shanaka de Silva b, Katherine A. Kelley c a Smithsonian Institution, National Museum of Natural History, Washington, DC 20560, USA b College of Earth, Ocean and Atmospheric Sciences, Oregon State University, Corvallis, OR 97331, USA c Graduate School of Oceanography, University of Rhode Island, Narragansett, RI 20882, USA a r t i c l e i n f o a b s t r a c t Article history: The composition of the continental crust is closely tied to subduction zone magmatism. Elevated oxygen Received 8 July 2015 fugacity ( f O2) plays a central role in fostering crystallization of oxide minerals and thereby aids in Received in revised form 21 January 2016 generating the calc-alkaline trend of iron depletion that characterizes the continents. Along continental Accepted 24 January 2016 margins, arc magmas erupt through continental crust and often undergo extensive differentiation that Available online 22 February 2016 may modify magmatic f O2. The importance of the subducting slab and mantle wedge relative to Editor: T.A. Mather the effects of this differentiation on the f O2 recorded by continental arc magmas remains relatively Keywords: unconstrained. Here, we focus on the effect of differentiation on magmatic f O2 using a suite of 14 Central Andean volcanic zone samples from the Central Volcanic Zone (CVZ) of the Andes where the continental crust is atypically thick crustal assimilation (60–80 km). The samples range in composition from ∼55 to 74 wt% SiO2 and represent the Neogene oxygen fugacity history of the arc. Samples are basaltic andesite to rhyolite and span a range of radiogenic isotopic subduction 87 86 compositions ( Sr/ Sr =∼0.705–0.712) that represent 30 to 100% crustal assimilation. We use several wet chemistry 3+ proxies to estimate the f O2 recorded by lavas, pumice, and scoria: (1) whole rock Fe /ΣFe ratios, (2) 3+ Fe /ΣFe ratios in quartz-hosted melt inclusions, and (3) Fe–Ti oxide oxygen-barometry. Comparison 3+ of the f O2 calculated from bulk Fe /ΣFe ratios (post-eruptive) with that derived from Fe–Ti oxides 3+ or melt inclusion Fe /ΣFe ratios (pre-eruptive), enables us to quantify the effect of syn- or post- eruptive alteration, and to select rocks for bulk analysis appropriate for the determination of pre-eruptive magmatic f O2 using a strict criterion developed here. Across our sample suite, and in context with samples from the literature, we do not find evidence for systematic oxidation due to crystal fractionation or crustal contamination. Less evolved samples, ranging from 55 to 61 wt% SiO2, record a range of >3 orders of magnitude in f O2, spanning the f O2 range recorded by all samples in our suite. Among these less evolved magmas, we find that those erupted from volcanic centers located closer to the trench, closer to the Benioff Zone, and with more geochemical evidence of subducted components in the mantle source (elevated La/Nb) result in magmas that record systematically higher f O2. We conclude that the slab/mantle source can exert greater control on magmatic f O2 than processes occurring in even the thickest continental crust. Thus, the f O2 of arc magmas, and hence their calc-alkaline nature, may be inherited from the mantle. © 2016 Elsevier B.V. All rights reserved. 1. Introduction more oxidized than tholeiites, no consensus exists on the oxida- tion mechanism. Degassing, fractional crystallization, and crustal The chemistry of arc magmas is intimately linked to the gener- contamination – all mechanisms of differentiation – have been ation of continents (Gill, 1981). Oxygen fugacity ( f O2) contributes suggested as possible vehicles for oxidation (e.g., Lee et al., 2005). to the creation of the calc-alkaline magmatic trends that typify Several studies have looked for magmatic oxidation due to de- arcs (e.g., Brounce et al., 2014; Kennedy, 1955; Osborn, 1959). gassing of C, H and S species in natural systems, but either have Despite the observation that calc-alkaline magmas are generally not observed it (Brounce et al., 2014; Cottrell and Kelley, 2011; Crabtree and Lange, 2012; de Moor et al., 2013; Kelley and Cot- trell, 2012)or have discovered degassing-induced magmatic re- * Corresponding author at: Smithsonian Institution; Mineral Sciences, NHB 119; TH duction (Anderson and Wright, 1972; Kelley and Cottrell, 2012; 10 & Constitution Ave, NW, Washington, DC 20560, USA. Tel.: +1 440 725 4144; fax: +1 202 357 2476. Moussallam et al., 2014; Shorttle et al., 2015). Low pressure frac- E-mail address: [email protected] (S.B. Grocke). tional crystallization can result in moderate oxidation of less than http://dx.doi.org/10.1016/j.epsl.2016.01.026 0012-821X/© 2016 Elsevier B.V. All rights reserved. S.B. Grocke et al. / Earth and Planetary Science Letters 440 (2016) 92–104 93 Fig. 1. The Central Volcanic Zone (CVZ) in the Andes of South America. Centers sampled span the entire CVZ and represent the complete range of 87Sr/86Sr ratios as shown in the legend. Numbers refer to crustal thickness and are from Allmendinger et al. (1997). Base map from www.geomapapp.org, Ryan et al. (2009). half a log unit (Cottrell and Kelley, 2011)but cannot explain the 2. Geologic background disparity between the oxidation states of oceanic arc and mid- ocean ridge rocks (Brounce et al., 2014; Crabtree and Lange, 2012; The present N–S oriented cordillera of the Andes is the re- Kelley and Cottrell, 2012). Crustal contamination (assimilation or sult of ∼200 My of subduction of the Nazca plate (Fig. 1). The partial melting of the host rock) can serve to reduce magmas (e.g., Central Volcanic Zone, or CVZ, of the Central Andes lies above Hine et al., 1978), oxidize magmas (e.g., Ague and Brimhall, 1988), exceptionally thick crust (up to 80 km; Beck et al., 1996; Yuan or produce no net change in oxidation state (e.g., Chappell and et al., 2002; Appendix A.1), created by horizontal shortening of White, 2001), depending on the composition of the material be- a thermally softened lithosphere, which uplifted the Altiplano– ing assimilated. The effects of crustal contamination on magmatic Puna plateau (Allmendinger et al., 1997; Isacks, 1988). Intense and voluminous caldera-forming eruptions formed the Altiplano– f O2 are therefore not easily generalized and remain understudied. Puna Volcanic Complex (APVC; de Silva, 1989a; de Silva et al., At continental arcs these processes have not been systematically 2006). The dominantly dacitic ignimbrites throughout the Cen- evaluated and may operate to modify magmatic f O2. tral Andean Neogene Ignimbrite Province, with basaltic andesite To investigate an end-member case, we examine the hypothesis as a minor component, belong to a high-K, calc-alkaline suite and that Central Andean magmas derive their oxidized nature from dif- have chemical and isotopic characteristics that suggest subduction- ferentiation within an extremely thick continental crust. We focus related mafic magmas variably contaminated by continental crust, on volcanic samples from the Central Volcanic Zone (CVZ) of the the most contaminated being those in the APVC (de Silva et al., Andes in South America, where magmas have ascended through 2006; Folkes et al., 2013; Kay et al., 2011; Ort et al., 1996; Ap- up to 80 km of continental crust (Fig. 1). CVZ volcanic rocks under pendix A.1). “Baseline” isotopic compositions of 87Sr/86Sr ratios consideration here have undergone variable amounts of differen- of ∼0.706 and 144Nd/143Nd ratios of ∼0.5124 record minimal tiation as measured by their silica contents (basaltic andesite to crustal contamination (Burns et al., 2015; Davidson et al., 1991; rhyolite with ∼55–74 wt% SiO ; Tables 1 and 2) and radiogenic 2 de Silva et al., 2006; Hildreth and Moorbath, 1988). Extension 87 86 =∼ strontium isotopes ( Sr/ Sr 0.705–0.712, Table 1; Davidson of the baseline compositions to more “crustal” values indicates et al., 1991; Davidson and de Silva, 1995; Folkes et al., 2013; the significant leverage that continental crust exerts on isotopic Kay et al., 2011; Trumbull et al., 1999). compositions, with some extreme CVZ magmas nearing assimilant We use two proxies for f O2 to evaluate the oxidation state compositions (Fig. 2; de Silva, 1989b; Hawkesworth et al., 1982; 3+ = of arc magmas from the CVZ: the Fe /ΣFe ratio (where ΣFe Klerkx et al., 1977). 3+ 2+ Fe + Fe ) as determined on bulk rocks by wet chemistry or as measured directly in glassy melt inclusions using Fe K-edge X–ray 3. Geochemistry of CVZ magmas and sample selection absorption near-edge structure (XANES) spectroscopy, and the f O2 determined from magnetite–ilmenite pairs. We provide quantita- We chose samples that represented the maximum possible tive documentation of the effect of differentiation on the f O2s range of crustal differentiation in the CVZ. The samples represent recorded by CVZ magmas. We explore the extent to which crustal 10 different volcanic centers and capture a large range of eruptive processes versus modifications to the mantle wedge may be re- styles and products, compositions, and crystal contents (Table 1; sponsible for inducing calc-alkaline magmatism. Table A.1). We selected petrographically and geochemically well- 94 Table 1 CVZ volcanic systems sampled with composition and petrographic information. b 87 86 Source Volcano/ Ref Sym Deposit Sample # Eruptive Sample Comp SiO2 Sr/ Sr Crystal Phenocryst Comments Caldera phase material (wt%) (error) (%) assemblage a a Calderas Guacha Caldera Gf Tara Fall 09008 Plinian Pumice Rhy 73.91 0.710281(11) 10 plg > qtz >> bt > pyx White > ksp > ilm > zr, ap a Gig Tara IG LA1 Ignimbrite Pumice Rhy 70.69 0.710562(13) 30 plg > qtz > am > bt Orange > ksp > MI >> zr, ap a Purico P Purico Fall 09006 Plinian Pumice Rhy 69.43 0.70901(25) 10 plg > bt > am > opx White >> ap, zr S.B.
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